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An Estimate of Tidal and Non-Tidal Modulations of Plate Subduction

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An Estimate of Tidal and Non-Tidal Modulations of Plate Subduction Tanaka et al. Earth, Planets and Space (2015) 67:141 DOI 10.1186/s40623-015-0311-2 FRONTIER LETTER Open Access An estimate of tidal and non-tidal modulations of plate subduction speed in the transition zone in the Tokai district Yoshiyuki Tanaka1*, Suguru Yabe2 and Satoshi Ide2 Abstract Non-volcanic tremors and slow slip events in subduction zones have been found to be triggered by small external stress disturbances, as demonstrated by the synchronization of temporal variations in tremor rate with diurnal and semi-diurnal tides. Therefore, long-term variations in tremor rate might be predicted by amplitude modulations of diurnal and semi-diurnal tides at decadal time scales. Given that tremors and slow slips are shear slip on the plate boundary, their long-term variations must be associated with fluctuations in plate subduction speed below the seismogenic zone. In previous work, we showed a good correlation between long-term seismicity and empirically calculated tremor rate based on observed tidal levels in the Nankai region, western Japan. Here, we present an improved method of modeling long-term slip rate fluctuation based on the calculation of Coulomb stress due to ocean and solid earth tides on the plate interface. We also include the effects of non-tidal ocean variations, such as the Pacific Decadal Oscillation and the Kuroshio Current, employing an ocean model developed by the Japan Meteorological Agency. We apply the method to the Tokai district, where the effects of the Kuroshio Current are large, and demonstrate the importance of considering non-tidal effects. Our calculated slip rate fluctuations could amount to 1 mm/year in decadal scales, and periods with faster rates partly corresponded to variations in seismicity. Slow slip events in the study region weakly corresponded to times of higher stress. Keywords: Tides; Slow slip; Tremors; Earthquake; Seismicity; Crustal deformation; Ocean bottom pressure; Pacific Decadal Oscillation; Kuroshio Current Findings unstable slip. Below the transition zone, slip is always stable, Introduction and the oceanic plate is subducted at a constant velocity. In Recent seismological and geodetic observations have thetransitionzone,thepresenceofhigh-pressurefluids revealed diverse shear slip patterns on plate subduc- due to dehydration of the subducted slab reduces the effect- tion interfaces (Ide et al. 2007a; Ide et al. 2007b), in- ive normal stress (e.g., Kodaira et al. 2004; Peacock 2009). cluding non-volcanic tremors and slow slip events In such cases, a conditionally stable regime can exist, (SSEs) (Obara 2002; Shelly et al. 2006, 2007; Schwartz and even small stress disturbances can trigger tremors and Rokosky 2007; Beroza and Ide 2011; Vidale and and SSEs, which are caused by remote earthquakes and di- Houston 2012). These events occur in the transition urnal and semi-diurnal tides (e.g., Miyazawa and Mori zone at depths of 30–40 km, where the frictional property 2006; Nakata et al. 2008; Rubinstein et al. 2008; Lambert on the plate interface changes from unstable to stable et al. 2009; Houston 2015). (Scholz 2002). In the seismogenic zone located just above Stress disturbances due to tremors and SSEs can trigger a the transition zone, the plate interface is locked partially, major rupture on the plate boundary by providing a final and stress accumulated due to plate motion releases with push (Dragert et al. 2004; Beroza and Ide 2011), and inter- actions between these slow events and the major rupture * Correspondence: [email protected] zone have been actively studied using numerical simula- 1Earthquake Research Institute, University of Tokyo, 1-1-1 Yayoi, Bunkyo-ku tions (e.g., Matsuzawa et al. 2010; Segall and Bradley 2012). 113-0032, Tokyo To perform such simulations, the frictional properties on Full list of author information is available at the end of the article © 2015 Tanaka et al. Open Access This article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made. Tanaka et al. Earth, Planets and Space (2015) 67:141 Page 2 of 11 the plate boundary must be known. One advantage of tremor rate was dominated by an 18.61-year periodic vari- observing the tidal responses of tremors is that a por- ation, which was generated by modulations of diurnal and tion of the frictional properties in the transition zone semi-diurnal tides. Long-term changes were well correlated at large spatial scales can be inferred, which is difficult with background seismicity during the period spanning to determine using laboratory experiments. The obtained from 1965 to 2010 in the Nankai Trough. Historical large properties can also be employed in numerical simulations earthquakes in this region also tended to occur when of earthquake cycles by assimilating observational data the predicted tremor activity with the 18.61-year period (e.g., Hori et al. 2014), which allows for more precise was high (IT2014). long-term forecasts of large earthquakes in each antic- However, in IT2014, tidal and non-tidal effects were not ipated region. In addition, tidal response measurement separated, and steric components were included because is useful for precisely monitoring small episodic stress the model was based on observational tide-level data. In changes (Nakata et al. 2008). this study, the effects of non-tidal variations in OBP on the On the other hand, some studies have reported the pres- slip rate in the transition zone were calculated for the first ence of seasonality and possibility of decadal time- time. For this estimate, a slip response model was applied scale periodicity in the seismicity of large earthquakes to the Tokai district as an example. Fluctuations of the slip in Japan (e.g., Ohtake and Nakahara 1999; Heki 2003; rates were demonstrated, and the importance of including Tanaka 2014). These statistical behaviors indicate the non-tidal effects in comparisons with variations in seis- presence of wide-area stress disturbances, and the ef- micity was noted. fects of these disturbances on the seismogenic zone have been investigated. Currently, only Heki (2003) has suc- cessfully explained the seasonality in northern Japan quan- Methods titatively by using a snow-load model. The effects due to Method for computing slip rate seasonal variations in atmospheric pressure are too small IT2014 presented the idea that tremors triggered by tides to trigger earthquakes (Ohtake and Nakahara 1999). Heki promote plate subduction in the tremor zone (Ide et al. (2004) mentioned that ocean loading models have unce- 2007b), which activates seismicity of shallower earth- rtainties due to steric (i.e., irrelevant with mass changes) quakes. In contrast to Beeler and Lockner (2003), who components and that in situ observations of ocean bottom reported that diurnal tides cannot trigger earthquakes pressure (OBP) are necessary for its correct estimation. based on data from laboratory experiments, tremors were Kataoka (2007) estimated seasonal variations in OBP by found to show tidal sensitivities at such high frequencies in using the Estimating the Circulation and Climate of the the Nankai Trough (Yabe et al. 2014), which can indirectly Ocean (ECCO; http://www.ecco-group.org) model and trigger earthquakes. In the current study, this idea is gener- concluded that the amplitudes are insufficient for trig- alized under the assumption that plate subduction speed in gering earthquakes. Currently, such external stress distur- the transition zone, including in slow slip areas, changes bances due to climatic effects have not been incorporated due to external forces. However, to prove that fluctuations in the above numerical simulations of earthquake cycles. in subduction speed below the seismogenic zone can trig- However, in the abovementioned studies, which attempted ger earthquakes, quantitative simulations, such as those to explain the periodicities in seismicity, the high sensitivity made by Hirose and Maeda (2013), would be necessary to of the transition zone to external stress disturbances calculate the 3-D stress distribution on the plate interface. was neglected. When considering their effects on the The stress behaviors would strongly depend on given transition zone, it is possible that smaller stress distur- frictional parameters, and enormous efforts are needed bances trigger tremors and SSEs, which trigger earthquakes. to reveal the parameter sensitivity. In this paper, as a first However, the long-term variations in the occurrence step in producing such simulations, the influences of ex- of tremors and SSEs were not studied until recently. ternal forces, which serve as inputs, are estimated using Pollitz et al. (2013) applied a hydrologic-loading model the empirical model from IT2014, with the number of pa- to explain the periodicity of slow events and the departures rameters being kept small. from periodicity at Vancouver Island, which lies in the The Tokai district is located on the east end of the Cascadia subduction zone. Ide and Tanaka (2014) (ab- Nankai Trough, where the Philippine Sea Plate subducts breviated as IT2014 hereafter) reported the possibility beneath the Eurasian (Amurian) Plate (Fig. 1a), which that tides could trigger tremors at the seasonal scale by ap- is magnified in Fig. 1b. The anticipated source area of a plying an empirical relationship between observed tremor megathrust earthquake is surrounded by the thick black rates and tide-gauge records at Seto Inland Sea. Fur- curve. The black dots and the green circle denote the thermore, IT2014 estimated a multi-decadal variation epicenters of tremors (Idehara et al. 2014) and the area in tremor rate by focusing on long-term modulations of where a large slip occurred due to a long-term SSE from tidal amplitudes (Section 4.2.2 in Pugh 1987).
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